. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography IOTTOM STRESS 61 40° 35< 30c. CORANGE UNES 70° FIGURE 8. Theoretical cotidal chart for the Mj semidaily tide of] the east coast. The cotidal lines are in hours after the Greenwich transit of the M2 moon. From Redfield (1958). The tidal currents are parallel to shore (v = 0). At a latitude of 45° and with a depth of 50 m, a Kelvin wave decays to e~x () of its magnitude at the coast in a distance y = c/f of 286 km. Conversely, a Kelvin wa
. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography IOTTOM STRESS 61 40° 35< 30c. CORANGE UNES 70° FIGURE 8. Theoretical cotidal chart for the Mj semidaily tide of] the east coast. The cotidal lines are in hours after the Greenwich transit of the M2 moon. From Redfield (1958). The tidal currents are parallel to shore (v = 0). At a latitude of 45° and with a depth of 50 m, a Kelvin wave decays to e~x () of its magnitude at the coast in a distance y = c/f of 286 km. Conversely, a Kelvin wave propagating at 45°N along a continental shelf 150 km wide with a depth of 50 m has a tidal amplitude 59% of the amplitude at the coast. A Kelvin wave propagating around a sea or ocean produces an amphidromic system. When a Kelvin wave enters an embayment in the northern hemisphere, such as the North Sea, it propagates counterclockwise around the embayment with the maximum tides and currents nearshore. Because the Kelvin waves do not decay rapidly away from their respective coasts, the motion at any given location is a combination of Kelvin waves. As a result, the tidal currents may not be colinear with the bathymetry. The sense of rotation of the tidal current direction is counterclockwise in this case, which is opposite to the direction for a Poincare wave on a continental shelf. 209 BOTTOM STRESS Bottom stress modifies tides and tidal currents;^ its effect is greatest where strong tidal currents occur in shallow water. To model quantitatively the stress applied by the sediment on the water above, the flow is assumed to consist of a slowly varying tidal current superimposed on turbulence. The distribution of turbulent stress within the water determines the varia- tion of tidal currents with distance above the bottom (velocity profile) and the dissipation of tidal energy. The details of flow near the bottom and estimates of bottom stress are central to the study of sedim
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